Miocene deep-water agglutinated foraminifera from
ODP Hole 909c: Implications for the paleoceanography
of the Fram Strait Area, Greenland Sea
1
Michael A. Kaminski1, Lóránd Silye2 and Severyn Kender3
Department of Earth Sciences, University College London, Gower Street, London WC1E 6BT, U.K.
email: m.kaminski@ucl.ac.uk
2Department of Geology, Babes-Bolyai University, Str. Kogalniceanu 1, 400084, Cluj-Napoca, Romania
3
Department of Earth Sciences, University College London, Gower Street, London WC1E 6BT, U.K.
email: s.kender@ucl.ac.uk
ABSTRACT: Deep-water agglutinated Foraminifera (DWAF) are investigated from Miocene sediments recovered from ODP Hole
909C in the Fram Strait, Norwegian-Greenland Sea. We studied 125 samples from Cores 909C-50R to –103R, and recovered over 60
species of DWAF. The faunal succession in Hole 909C is subdivided into three assemblages based on the stratigraphic ranges of characteristic cosmopolitan taxa. These are: (1) a diverse Reticulophragmium amplectens – Reophanus berggreni Assemblage in Cores
909C-100R-2 to -91R-1 (1040.71–952.78mbsf); (2) a Reticulophragmium amplectens Assemblage in Cores 909C-87R-2, to -71R-3
(915.7–762.68mbsf); and (3) a low-diversity Reticulophragmium rotundidorsatum Assemblage in Cores 909C-71R-1 to -55R-1
(759.68-605.52mbsf). The DWAF assemblages are correlated to the standard chronostratigraphy using dinoflagellate cysts and
magnetostratigraphy. The stratigraphic ranges of some well-known Paleogene DWAF species extend far into the Miocene at this locality, confirming the hypothesis that the Arctic and northern Norwegian Sea basins served as a refuge for these species long after they disappeared from the North Atlantic stratigraphic record. The taxonomic affinities of the Miocene assemblages from Hole 909C supports
the idea that an estuarine circulation pattern has been in place between the Arctic Ocean and Greenland Sea basins since at least the early
Miocene. Changes in the benthic foraminiferal morphogroups within the R. rotundidorsatum Assemblage correlate with an increase in
total organic carbon, indicating an increase in oceanic productivity in the Fram Strait region during the late Miocene.
INTRODUCTION
Deep-water agglutinated foraminifera, commonly known by
the acronym DWAF, represent one of the most useful groups of
microfossils for stratigraphical and paleoenvironmental interpretations of high-latitude Cretaceous to Miocene deep-water
sedimentary sequences. They are often the only benthic microfossils preserved in the deep-water deposits of the Boreal seas.
Key studies carried out to date on the DWAF of the northern
North Atlantic region almost exclusively dealt with the taxonomy and biostratigraphy of Paleogene taxa (Gradstein and
Berggren 1981; Miller et al. 1982; Verdenius and van Hinte
1983; Gradstein and Kaminski 1989, 1997; Gradstein et al.
1994, Kaminski et al. 1990; Kaminski and Geroch 1997; Nagy
et al. 1997, 2000, 2004; Kaminski and Austin 1999). The fact
that so few studies have been carried out on the Neogene
DWAF from the North Atlantic is a consequence of either the
lack of Miocene recovery and/or well-preserved Miocene agglutinated foraminiferal assemblages from most drilled locations. Miocene sediments from the Central Norwegian Sea are
often biosiliceous, and therefore unfavourable for DWAF preservation. An exception to this was the discovery of well preserved and anomalously young Miocene DWAF in ODP Hole
909C drilled in the Fram Strait area of the Greenland Sea, published in the scientific results of the ODP Leg 151 “North Atlantic-Arctic Gateways” expedition (Osterman and Spiegler
1996).
The Fram Strait is a critical ocean “gateway” – it is the only
conduit to exchange deep waters between the Arctic and the At-
lantic Oceans. One of the primary objectives of drilling at Site
909 was to document the timing of the opening of a deep passageway through the Fram Strait, and the history of deep and
shallow water exchange between the Arctic and the world ocean
(Thiede and Myhre 1996). The DWAF of ODP Hole 909C
therefore play a crucial role for our understanding of faunal and
water mass exchange between the Norwegian-Greenland Sea
and the Arctic Ocean. Moreover, this fauna may be useful for
biostratigraphical correlation between the North Atlantic and
the Arctic IODP holes. The proposed ages for the opening of the
Fram Strait gateway span from the early Oligocene, Anomaly
13, to the late Miocene, Anomaly 5 (Thiede and Myhre 1996).
However, the Fram Strait has a strongly oblique opening and is
in the proximity of the submerged Hovgård Microcontinent,
which may have acted as a plug until the Miocene (Myhre and
Thiede 1995, Thiede and Myhre 1996). This makes it more difficult to estimate the timing of the opening of the Fram Strait
and the initiation of deep-water connections between the Norwegian-Greenland Sea and Artic Ocean.
The main objectives of this study are to (1) revise the taxonomy
of the benthic foraminifera recovered from ODP Hole 909C; (2)
provide a continuous biostratigraphic and proxy record for
sea-floor conditions during the Miocene; (3) establish the sequence of benthic foraminiferal assemblages that will contribute to our understanding of Artic biota from the Eocene to late
Miocene; (4) test whether agglutinated foraminifera can be used
to interpret the history of deep water connections between Norwegian Sea and Arctic Ocean through the Fram Strait; and (5) to
micropaleontology, vol. 51, no. 5, pp. 373-403, 2005, text-figures 1-5, plates 1-7, appendix 1 (2006)
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M. A. Kaminski et al.: Miocene foraminifera from ODP Hole 909c: Paleoceanography of the Fram Strait Area, Greenland Sea
better understand the paleoproductivity and the timing and onset of deep convection in the Fram Strait region.
Toward these aims, the agglutinated foraminiferal record from
Hole 909C in the Fram Strait is particularly important to test the
hypothesis that the Arctic may have served as a refuge, for certain species as previously suggested (Kaminski et al. 1990,
Osterman and Spiegler 1996). This hypothesis could explain
why typical agglutinated Paleogene species have been found in
younger sediments in the Arctic. We wish to assess to what degree faunas in the Fram Strait area are endemic, and whether
they contain any typical Arctic species. However, these latter
questions can only be fully answered after the scientific results
of IODP drilling in the Arctic Ocean are published.
BACKGROUND
Location
ODP Site 909 is located in the southern area of the Fram Strait
near the Greenland-Spitsbergen sill terrace immediately north
of the Hovgård Ridge (Myhre and Thiede 1995). This gently elevated area is protected against the influx of turbidites from the
Svalbard and Greenland margins (Shipboard Scientific Party
1995). Hole 909C was drilled on a small abyssal terrace of the
Fram Strait, at 78o35.096´N, 3o4.222´E (text-fig. 1), at a water
depth of 2518 m (drill pipe measurement from sea level), with a
penetration of 1061.8mbsf. The total length of cored section
was 976.8m, with an average core recovery of 61.9% (Shipboard Scientific Party 1995).
Lithology
The sediments recovered are dominated by silty clay throughout the entire cored section. Clay, clayey silt, clayey mud, and
silty mud are also common. Calcareous clays and carbonate-bearing silty clays, containing thin layers and nodules of inorganic carbonates are characteristic, and are present in small
quantities throughout the sedimentary sequence. However,
biogenic sediments are present only in specific intervals as trace
components. Dropstones occur only in the interval of 85.8314.26mbsf, dated to the early Pliocene (4.6 Ma.) to Recent by
means of the magnetic polarity record (Shipboard Scientific
Party 1995).
Three lithologic units were recognized in Hole 909C (Shipboard Scientific Party 1995). The agglutinated foraminiferal assemblages described here appear within Unit III (518.31061.8mbsf), which is subdivided into Lithologic Subunit IIIA
(518.3–923.4 mbsf) and Lithologic Subunit IIIB (923.4mbsf–
1061.8mbsf). These subunits were correlated to the Miocene,
based on magnetostratigraphy and the occurrence of latest
Oligocene/earliest Miocene calcareous nannofossil assemblage
at the base of the hole, and the continuous occurrence of Miocene dinoflagellate cysts below Core 23R (Hull, et al. 1996;
O’Connell et al. 1996; Poulsen et al. 1996).
The sediments of Subunit IIIA (Cores -46R-1 through
-87R-CC) are dominated by very dark gray silty clay, with
coarser grains at the base. The top of the subunit is placed at
518.3mbsf, defined by the presence of laminations below this
horizon. Clayey silt, silty mud, several meters-thick intervals of
carbonate, and carbonate-bearing sediments (concretions) are
also present as minor constituents. Lamination is a characteristic feature of this subunit. Very dark gray laminae are generally
interlayered with dark grayish brown, grayish brown, and light
brownish gray laminae. Bioturbation is observed throughout al-
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most the entire section. Even within the best-developed laminae
rare burrows can be observed. Many originally laminated intervals are extensively bioturbated, and the burrows parallel to
bedding plane appear to enhance rather than obscure the laminations. The thin laminations of the Subunit IIIA were possibly
caused by rhythmic depositional processes, extending over 15
million years (Shipboard Scientific Party 1995).
The sediments of Subunit IIIB (Cores -88R-1 through
-103R-CC) are distinguished from the overlying sediments by
the presence of slump structures. The slumps exhibit sharp basal
contacts and millimeter- to tens of meter-scale folds, rip-up
clasts, tilted and pinched layers. Sometimes the disturbed layers
have sharp upper contacts. The slumps are interpreted as results
of rapid sediment accumulation and small textural differences.
Bioturbation is generally moderate to extensive, but is absent
from the thickest slumps. The most important sediments of the
subunit include grayish brown, olive gray, dark greenish gray,
dark gray colored silty clay, clayey silt, mud, and silty mud. Agglutinated and rare calcareous benthic foraminifera are present
in the sediments of Subunit IIIB. The calcareous foraminifera
are usually decalcified, and many of the agglutinated specimens
are fragmented (Shipboard Scientific Party 1995).
Biostratigraphy
The age control of Hole 909C is accomplished by means of
planktonic foraminifera, calcareous nannofossils, and palynomorphs (Spiegler 1996; Hull et al. 1996; Poulsen et al. 1996).
Magnetic polarity records have also been used (O’Connell et al.
1996). The chronostratigraphy of the studied interval is summarized in text-figure 2.
The oldest sediments recovered from Hole 909C are regarded to
be earliest Miocene based on the occurrence of the calcareous
nannofossil Helicosphaera carteri in Sections 909C-101R-2 to
102R-CC (Shipboard Scientific Party 1995). Dinocysts also
support an early Miocene (Aquitanian?-Langhian?) age based
on the occurrence of Hystriochokolpoma sp. 2 in Sample
909C-103R-CC (Poulsen et al. 1996). This species was not recorded below the Miocene at Site 643 (Manum et al. 1989).
Middle Miocene (Langhian-Serravallian) sediments occur in
dinocyst Zone Mio2 (Langhian), Mio3 (Langhian-Serravallian)
and Mio4 (Serravallian). Zone Mio2 is defined between the FO
(first occurrence) of Labyrinthodinium truncatum in Sample
909C-98R-CC (1020.0mbsf), and the LO (last occurrence) of
Apteodinium spiridoides identified in Sample 909C-95R-CC
(992.0mbsf). Zone Mio3 is present up to the LOs of Apteodinium australiense and Distatodinium paradoxum in Samples
909C-87R-CC (916.23mbsf) and 81R-CC (861.78 mbsf), respectively. However, based on the FO of Achomosphera?
andalousiensis in Sample 909C-82R-CC, the upper boundary of
this dinocyst zone is placed at the FO of Achomosphera?
andalousiensis, and not at the LO of Distatodinium paradoxum.
The lower boundary of Zone Mio4 is placed at the FO of
Achomosphera? andalousiensis in Sample 909C-82R-CC
(867.8mbsf), whilst the top of the zone is defined by the LO of
Systematophora placacantha in Sample 909C-70R-CC
(Poulsen et al. 1996).
A Late Miocene (Tortonian) age is assigned to Zone Mio5, the
upper boundary of which is defined by the LO of Paleocystodinium golzowense in Sample 909C-51R-CC, at
573.01mbsf (Poulsen et al. 1996). From 345.3 to 566.6mbsf
(Samples 909C-27R-CC to 50R-CC) Upper Miocene to lower
Micropaleontology, vol. 51, no. 5, 2005 (2006)
TEXT-FIGURE 1
Location of ODP Leg 151 Sites 907-913 (modified after Thiede and Myhre 1996).
Pliocene sediments have been reported (Hull et al. 1996;
Poulsen et al. 1996).
Planktonic foraminifera in Hole 909C were studied by Spiegler
(1996). According to these data, planktonic foraminifera are
very rare in Hole 909C, owing to dissolution. Below Core
909C-43R, only about 10% of samples contained planktonic
foraminifera. In Sample 909C-76R-1, 96-98cm (808.56mbsf)
the FO of Globigerina bulloides indicates a late Miocene age,
whilst in Sample 909C-89R-1, 97-100cm (934.07mbsf) the FO
of Orbulina universa indicates a Middle Miocene or younger
age (Spiegler 1996). No planktonic foraminifera were recovered in this study.
The agglutinated foraminifera from Hole 909C were initially
studied by Osterman and Spiegler (1996). Agglutinated foraminifera were found to occur more or less continuously from the
base of the hole up to Core 909C-52R,CC, and four assemblages are recognised. From the oldest to youngest these are:
(1) A lower to middle Miocene Rhabdammina/Reophax assemblage (Samples 151-909C-100R-CC to -103R-CC; 1048.4 to
1062.8mbsf).
(2) A middle Miocene Reticulophragmium ex gr. rotundidorsatum and R. amplectens assemblage (Samples 151-909C90R-CC to -100R-1, 95-99cm; 952.4 to 1039.75mbsf).
(3) A middle Miocene Reticulophragmium amplectens assemblage (Samples 151-909C-71R-CC, 95-99cm, to -87R-CC;
760.25 to 923.4mbsf).
(4) A middle to upper Miocene Reticulophragmium ex gr.
rotundidorsatum assemblage (Samples 151-909C-51R-1, 7678cm, to -70R-CC; 605.86 to 759.3mbsf).
Osterman and Speigler (1996) noted that Reticulophragmium
amplectens is normally an Eocene species that had not been previously reported in sediments of Miocene age. These authors
excluded the possibility of reworking because (1) the site is located on a submarine high, and substantial tectonic uplift would
be required to allow the erosion of Eocene deep water deposits
and subsequent redeposition into Miocene sediments. Such a
situation has not been confirmed. (2) None of the other
microfossil groups recovered in this interval show signs of reworking, and all indicate a Miocene age (Osterman and Spiegler
1996; Hull et al. 1996). Additional foraminiferal taxa known
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M. A. Kaminski et al.: Miocene foraminifera from ODP Hole 909c: Paleoceanography of the Fram Strait Area, Greenland Sea
TEXT-FIGURE 2
Chronostratigraphy of Hole 909C, based on magnetostratigraphy (Shipboard Scientific Party 1995), palynology (after Poulsen et al. 1996), planktonic
foraminifera (after Spiegler 1996) and calcareous nannofossils (after Hull et al. 1996). Also shown are our agglutinated foraminiferal assemblages and
important last occurrences of DWAF. Arrows represent diversity/abundance (solid increasing, dashed decreasing).
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TEXT-FIGURE 3
Agglutinated foraminifera abundance and species number in Hole 909C (566.97 to 1040.71mbsf). Also shown are the proportions of some abundant and
biostratigraphically important taxa (Hyperammina rugosa, Haplophragmoides carinatus, R. amplectens. R. rotundidorsatum).
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M. A. Kaminski et al.: Miocene foraminifera from ODP Hole 909c: Paleoceanography of the Fram Strait Area, Greenland Sea
from Paleogene strata in the Norwegian Sea – North Sea region
were also reported.
MATERIALS AND METHODS
The standard methods of sample processing were applied to 125
samples collected from Hole 909C, from 566.97 to 1040.71
mbsf (Cores 909C-51R-1, 37-39cm through 100R-2, 4142.5cm, except Core 151-909C-79R). The average volume of
samples was 20cc, and the number of samples collected per
core was 2 or 3. Each sample was dried overnight at about
40-50oC and then boiled in water with sodium carbonate
(Na2CO3) until completely disaggregated (about 15-20 minutes). The disaggregated samples were washed over a 63-µm
sieve. The residues were retained and dried at about 40-50oC.
Foraminifera were picked from the entire >63-µm residue. The
specimens were photographed using a Zeiss 940 digital scanning electron microscope at Department of Earth Sciences, University College London.
RESULTS
DWAF Assemblages
The examination of samples from Hole 909C yielded 85 foraminiferal species and generic groupings (Appendix 1). The specimens throughout the studied interval are generally uncrushed
and well preserved. Abundance and diversity display maximum
values in the basal part of the studied interval (text-figure 3),
and both parameters display minima within the slumped interval represented by Samples 909C-90R-2, 40-41.5cm to -88R-1,
39.5-41cm. Above the slumped interval, abundance and diversity are variable, but no meaningful trends are observed until
679m. Above this interval preservation was patchy, and both
parameters decline upcore.
(2) Reticulophragmium amplectens Assemblage (Cores 909C87R-2, 40-42cm to -71R-3, 38-39.5cm; 915.7 to 762.7mbsf) is
found above a slumped interval (Samples 909C-90R-2,
40-41.5cm to -88R-1, 39.5-41cm). A rapid change in foraminiferal abundance (the lowest faunal abundances in Hole 909C)
is observed in this interval (text-figure 3).
This assemblage is characterized by the presence of Reticulophragmium amplectens (Grzybowski 1898), R. pussilum (Brady
1881), the absence of R. rotundidorsatum (Hantken 1875), and
the LOs of Nothia robusta (Grzybowski 1898), Aschemocella
grandis (Grzybowski 1898), Hyperammina elongata Brady
1878 and Saccammina cf. sphaerica Brady 1879.
(3) Reticulophragmium rotundidorsatum Assemblage (Cores
909C-71R-1, 38.5-40m to 55R-1, 41.5-43cm; 759.7 to 605.5
mbsf) is the stratigraphically youngest DWAF assemblage in
Hole 909C. The lower boundary of the assemblage is close to a
major faunal density minimum (text-fig. 3). This assemblage
was identified by Osterman and Spiegler up to Core
909C-55R-CC. We extend the upper boundary of this assemblage upwards to Core 909C-55R-1, where the LO of
Reticulophragmium rotundidorsatum (Hantken 1875) is observed. The faunal abundance and diversity declines upsection
through the middle to upper Miocene, and above Core –55R the
samples are barren of foraminifera. This assemblage contains
the LOs of Reticulophragmium amplectens (Grzybowski 1898),
Karreriella seigliei (Gradstein and Kaminski 1989), Repmanina
charoides (Jones and Parker 1860), Pseudonodosinella elongata (Grzybowski 1898), Psamminopelta gradsteini Kaminski
and Geroch 1997, and Spirosigmoilinella compressa Matsunaga
1955.
Palaeobathymetry and Paleoecology
(1) Reticulophragmium amplectens – Reophanus berggreni Assemblage (Cores -100R-2, 41-42.5cm to -91R-1, 38.5-40.5cm;
1040.7 to 952.8mbsf) is characterized by the co-occurrence of
Reticulophragmium rotundidorsatum (Hantken 1875), Reticulophragmium amplectens (Grzybowski 1898), Reticulophragmium pusillum (Brady 1881), and Reophanus berggreni
Gradstein and Kaminski 1997. Additionally, Recurvoides spp.,
Psamminopelta gradsteini (Kaminski and Geroch 1997),
Nothia robusta (Grzybowski 1898), Nothia latissima (Grzybowski 1898), and Hyperammina rugosa Verdenius and Van
Hinte 1983 are common in this interval. This assemblage has
the highest faunal density and diversity observed in Hole 909C
(text-fig. 3).
The study of agglutinated foraminiferal morphogroups has
much potential for palaeoenvironmental interpretation, as the
life position and the relative abundance of trophic groups are affected by various environmental parameters, such as organic
productivity and bottom-water oxygenation. As pointed out by
Jones and Charnock (1985); Nagy (1992); Nagy et al. (1995,
1997); and van den Akker et al. (2000), agglutinated foraminifera taxa can be grouped into “morphotypes” based on gross
morphology that are believed to reflect differences in the life
position and feeding habit. Morphotypes in turn can be combined into “morphogroups”, according to their preferred habitat
with respect to the sediment/water interface (e.g., infaunal vs.
epifaunal morphogroups). The morphogroup classification used
here (text-figure 4) is based on the work of Nagy et al. (1997)
and van den Akker et al. (2000). There is one difference between the study of van den Akker et al. (2000) and our morphogroups. In this study, the species Aschemocella sp., and
Aschemocella subnodosiformis are interpreted as belonging to
morphogoup M1 of the tubular forms, whilst the single chambers of Aschemocella grandis (only a few specimens have been
found) are included into morphotype M2a of the globular forms.
Although the foraminiferal assemblage is similar to that described by Osterman and Spiegler (1996) from the same interval, we prefer not to use their nomenclature for this assemblage
(Reticulophragmium ex gr. rotundidorsatum – R. amplectens
Assemblage), to avoid confusion. Moreover, the distinctive
species Reophanus berggreni Gradstein and Kaminski 1997 is
present only in this interval in Hole 909C (the species was probably lumped under Hormosinella carpenteri by Osterman and
Spiegler (1996)).
The agglutinated foraminiferal species in Hole 909C comprise
seven morphotypes belonging to four main groups (text-figure
4). The relative proportions of the morphotypes in Hole 909C
are presented in text-figure 5. The tubular taxa of morphogroup
1 (M1) are common throughout the studied sedimentary sequence, representing about 30-40% of the total number assemblage, with a lower (10-20%) proportion in the uppermost part
of the studied interval (above 762 mbsf). Nagy et al. (1997) interpreted variations in this morphogroup as a paleobathy-
The composition of DWAF in our samples displays strong similarities to the assemblages described by Osterman and Spiegler
(1996). Based on the ranges of distinctive taxa, we suggest the
following subdivision into three assemblages (from oldest to
youngest), here modified from Osterman and Spiegler (1996):
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TEXT-FIGURE 4
Morphogroup classification of agglutinated foraminifera found in Hole 909C (modified after van der Akker et al. 2000).
metrical indicator, as the tubular forms are most abundant in
continental slope and rise settings where particulate organic
matter is advected by gentle bottom currents. If this interpretation holds, the high proportions of M1 recovered at the base of
the drilled section imply that Site 909 had already subsided to
lower bathyal depths by the early Miocene. Based on plate tectonic reconstructions, Kristofferson (1990) speculated that shallow-water connections through the Fram Strait had already
opened by the mid Oligocene, subsiding to about 2km depth by
the middle Miocene. Our faunal data are in agreement with this
estimate. The first appearance of cosmopolitan benthic foram-
inifera in the upper Eocene to lower Oligocene of the Beaufort
Sea wells led McNeil (1990) to postulate a somewhat earlier
connection to the Atlantic Ocean.
Morphotype M2b (dominated by Recurvoides and related
forms) shows little overall trend, but has three broad maxima of
around 20% of the total fauna within intervals with lower proportions of M1. Recurvoides is a cosmopolitan genus, typical of
deep-water settings. Recurvoides is regarded by Gradstein et al.
(1994) as a typical indicator for middle and lower bathyal facies
in the North Sea.
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The most striking feature of the morphogroup analysis is the
trend displayed by morphotype M4a (shallow infauna and
surficial epifauna). This morphotype shows an inverse trend to
morphogroup M1, steadily increasing from an average of
20-30% of the assemblage below 762mbsf, to 60-80% in samples above 660mbsf. In the Paleogene sections of Spitsbergen
and the Barents Sea area, high abundances of this morphotype
are regarded by Nagy et al. (2000) as typical of shallower
depositional environments at middle to upper neritic water
depths. While we do not suggest here that the Fram Strait sill
experienced any significant tectonic uplift, it is important to
note that shallower depositional settings typically experience
higher rates of organic carbon flux. Therefore, it is more likely
that morphotype M4a is responding to changes in organic productivity rather than paleobathymetry.
The record of organic carbon values in Hole 909C reflect
changes in the supply of transported terrestrial organic matter
and the flux of marine organic matter from primary production.
The high TOC values at the base of Hole 909C reflect high
amounts of terrestrially-derived organic matter from the surrounding land masses (Knies and Mann 2002). In this part of
the section the proportion of morphotype M4a is small. Above
920mbsf the proportion of morphotype M4a increases concurrently with an increase in the percent TOC (values taken from
Stein and Stax 1996). The TOC values increase from an average of 0.8% in Core –70R (ca. 750mbsf) to values as high as 1.5
% in Core –55R (ca. 605mbsf). The low C/N values of the organic carbon over this interval (between 7 and 9) indicate a
strong marine component (Stein and Stax 1996). Stein and Stax
remarked that the unusually high flux of marine organic carbon
at Site 909 requires paleoceanographic conditions that are “different from normal open-ocean ones.”
It is noteworthy that the observed shift in the proportions of the
morphotypes M1, M2a, and M4a at 762mbsf coincides with the
reappearance of Reticulophragmium rotundidorsatum (and the
establishment of our Reticulophragmium rotundidorsatum Assemblage), suggesting that the distribution of the Reticulophragmium rotundidorsatum is environmentally controlled.
This fact becomes evident considering that in the lower part of
the section, R. rotundidorsatum is present in only a few samples
and in lower proportions (text-fig. 3) than in the upper part of
the section, above 762mbsf. This fact suggests that Reticulophragmium rotundidorsatum is sensitive to organic flux levels
or other parameters of the deep ocean environment.
DISCUSSION and CONCLUSIONS
The stratigraphic importance of the Miocene agglutinated foraminiferal fauna recovered from Hole 909C cannot be over-emphasized. Not only is Site 909 situated in a key oceanic
gateway, but DWAF species that are elsewhere recorded from
Paleogene sediments range into stratigraphically younger strata
at this locality. Osterman and Spiegler (1996) recorded several
species (e.g., Hyperammina rugosa, Nothia excelsa, Haplophragmoides porrectus) for the first time from Miocene deposits. In this study we document the youngest known occurrences
of some additional species, such as Reophanus berggreni and
Psamminopelta gradsteini (text-fig. 2; Appendix 1). In a study
of the Paleogene assemblages from ODP Hole 643A, Kaminski
et al. (1990) first pointed out the apparent diachrony of high-latitude agglutinated foraminifera with increasing latitude.
Schröder-Adams and McNiel (1994) also pointed out that a
number of cosmopolitan species such as R. amplectens, B.
multicamerata, R. rotundidorsatum and S. compressa became
380
extinct later (in the Miocene) in the Beaufort Sea–MacKenzie
Delta area than in the North Atlantic region.
In the North Atlantic petroleum basins, Paleocene to Eocene assemblages are predominantly agglutinated, Oligocene to Miocene assemblages usually contain varying proportions of
calcareous and agglutinated taxa, while the Miocene to Recent
assemblages are predominantly calcareous (Gradstein et al.
1994). This general faunal change has been widely interpreted
as representing the transition from the silled, stratified basins of
the Paleogene to more well oxygenated basins that allowed the
preservation of biogenic carbonate (Gradstein and Berggren
1981). According to this model, deep, cold, stratified basins
with high sedimentation rates favour preservation of the DWAF
assemblages. This is also the case with the anomalously young
Oligocene-Miocene DWAF assemblages documented by
Schröder-Adams and McNeil (1994) from the Beaufort Sea.
Osterman and Spiegler (1996) suggested a strong environmental control of the DWAF assemblages from Hole 909C to explain their occurrence in younger strata. They noted that the
optimum habitat of the DWAF possibly shifted northward, as
rifting in the North Atlantic progressed, creating high sedimentation-rate basins. The Miocene sediments at Site 909 are unusual in that they are organic rich, largely non-calcareous, and
reflect higher sedimentation rates than at other sites further to
the south. Furthermore, it may be the case that because of the
tectonic evolution of the Fram Strait and other sills further to the
south, this region was isolated from North Atlantic bottom waters during the Miocene. Because of this isolation and suitable
environmental conditions (without carbonate deposition), the
Paleogene DWAF faunas found a refuge in the Fram Strait region up to the late Miocene (Osterman and Spiegler 1996).
However, there is a need for further paleobiogeographical studies (including comparisons with microfossil assemblages from
the Beaufort Sea and the Arctic region) to fully clarify the problem of diachrony among agglutinated assemblages.
At present, the general oceanic circulation pattern between the
Arctic Nansen Basin and the Greenland Sea is estuarine, with
surface waters flowing out of the Arctic and warmer, more saline water of Atlantic origin flowing into the Nansen Basin at
depth. The presence of DWAF with Norwegian Sea affinities at
Site 909 strongly suggests that this estuarine circulation pattern
was in place by the Early Miocene. However, we need to compare the record from Site 909 with the new data obtained from
the Arctic Drilling Expedition (summer 2004) to fully resolve
this issue.
Today, the area of the comparatively warm, seasonally ice-free
West Spitsbergen Current to the west and north of Spitsbergen
is the most highly productive sector of the European Arctic region. Productivity declines rapidly to the west and to the north
of the current as the amount of ice cover increases, with highly
oligotrophic conditions present in the permanently ice-covered
Central Arctic Ocean (Wollenburg and Mackensen 1998). The
morphogroup analysis and sediment parameters from Hole
909C suggest that paleoenvironmental conditions in the Fram
Strait area were not stable during the Miocene. A shift in the
proportions of the agglutinated foraminiferal morphotypes is
observed alongside changes in the organic carbon flux at Site
909, in particular, the proportion of the planispiral morphotype
M4a appears to be positively correlated with the TOC content.
Stein and Stax (1996) speculated that variations in the West
Spitsbergen Current and in sea-ice cover through time may have
Micropaleontology, vol. 51, no. 5, 2005 (2006)
TEXT-FIGURE 5
Relative distribution (in percentage) of agglutinated foraminiferal morphotypes in Hole 909C (566.97-1040.71 mbsf). Also shown is the 3-point moving
average of percent Total Organic Carbon values in the studied section (data from Stein and Stax 1996).
been the dominant mechanism controlling the organic carbon
deposition at Site 909, which we think also influenced the proportions of the benthic foraminiferal morphotypes. Site 909 is
located on the bathymetric sill between the Norwegian-Greenland Sea and the Arctic Ocean, currently at ca. 2600m depth.
Allowing for normal thermal subsidence, the site would have
been shallower during the Miocene, and affected by surface and
intermediate waters of Atlantic origin. Any intensification of
the surface and intermediate water exchange over the Fram
Strait sill would have created locally increased upwelling conditions, leading to enhanced primary productivity. The location
of the ice margin is also important because of the occurrence of
ice-margin phytoplankton blooms (Smith and Nelson 1986).
The record of dinoflagellate cysts from Hole 909C (Poulsen et
al. 1996; fig. 3) shows increasing numbers of heterotrophic
forms such as Selenopemphix, Protoperidinium, and Lejeunecysta (forms that feed upon diatoms) over the same interval.
However, the micropalaeontological residues are devoid of any
planktonic microfossils, so it is not clear which planktonic organisms contributed to the productivity signal at Site 909.
Winkler et al. (2002) noted a change in the clay minerals and an
increase in bulk accumulation rate over this same interval in
Hole 909C, suggesting a provenance change in the terrigenous
component. At the same time, an increase in coal fragments, igneous and metamorphic rock fragments and mica content occur
(Wolf-Welling et al. 1996). These sedimentological changes
are regarded as reflecting an increase in the water mass exchange through the Fram Strait as well as seasonal ice rafting
(Winkler et al. 2002). Bohrmann et al. (1990) noted an intensification of bottom currents in the Vøring Plateau region (Sites
642 and 643) between 13 and 11 Ma, and linked this to the establishment of significant outflow over the Iceland-Scotland
Ridge.
The only other locality in the northern North Atlantic where
DWAF assemblages were documented from upper Miocene
sediments is at ODP Site 646 off the southern tip of Greenland
(Kaminski et al. 1989). In Hole 646A, the agglutinated assemblage occurs in the interval with the highest bulk sediment accumulation rate and TOC contents (see Bohrmann et al. 1990, fig.
6). This interval in Hole 646 was linked to the appearance of
Denmark Strait Overflow water at this locality at approximately
7.5 Ma. Interestingly, the DWAF assemblages disappeared
from the record of Hole 646A when biosiliceous sedimentation
commenced around 4 Ma (Kaminski et al. 1989; Bohrmann et
al. 1990).
We conclude that the “favorable” environment for the occurrence of Neogene DWAF assemblages in the northern North Atlantic involves the rapid accumulation of carbonate-poor
terrigenous sediments, moderate (not high) rates of organic carbon flux, and the absence of a significant biosiliceous component. The presence of gentle bottom currents probably also
plays a positive role, especially with regards to the suspension
feeding tubular morphogroup. At other Norwegian Sea sites
where Miocene sediments are biosiliceous, the DWAF assemblages are either absent or consist of only a few specialized taxa
(Verdenius and Van Hinte 1983, Kaminski et al. 1990). As
pointed out by previous authors (e.g., Gradstein and Berggren
1981; Ostermann and Spiegler 1996) such favorable sedimentary conditions can be found in the tectonically active high-latitude deep basins. The diversity of species and morphogroups in
Miocene DWAF assemblages appears to be a function of the
trophic continuum, and in particular the carbon flux (Preece et
al. 1999). Diversity is negatively correlated with carbon flux,
with larger numbers of agglutinated species occurring towards
the oligotrophic end of the trophic spectrum (Altenbach et al.
1999).
381
M. A. Kaminski et al.: Miocene foraminifera from ODP Hole 909c: Paleoceanography of the Fram Strait Area, Greenland Sea
ACKNOWLEDGMENTS
Ammodiscus cf. A. latus Grzybowski
We thank the Ocean Drilling Program Core Repository for providing samples from Hole 909C, and the NERC ODP committee for funding the current project (Grant NER/T/S/
2003/00037). Lóránd Silye thanks the EEC Socrates Programme and the Grzybowski Foundation (the Stanislaw Geroch
Memorial Scholarship Fund) for sponsoring his studies at UCL.
We thank Thomas M. Cronin (USGS), Jens Matthiessen
(AWI), and John Farrell (URI) for kindly pre-reviewing the paper, and Rachel Preece (Chevron) and Wolfgang Kuhnt (CAU)
for reviewing the final draft. This is contribution number 75 of
the Deep-Water Agglutinated Foraminiferal Project.
cf. Ammodiscus latus GRZYBOWSKI 1898, p. 282, pl. 10, figs. 27-28.
TAXONOMIC NOTES
Fragments are closest to Ammodiscus latus Grzybowski
Ammodiscus sp. 1
Plate 2, figure 2
Deformed or poorly preserved specimens, which are closest to
Ammodiscus tenuissimus Grzybowski.
Ammodiscus sp. 2
Plate 2, figure 1
Broken specimen resembling Ammodiscus cretaceus (Reuss).
The taxa below are listed alphabetically by genus. Species identifications are based largely on the taxonomic work of
Gradstein and Kaminski (1989, 1997), Charnock and Jones
(1990), Kaminski and Geroch (1993), Gradstein et al. (1994),
Kaminski et al. (1988, 1989, 1990), Schröder-Adams and
McNeil (1994), Osterman and Spiegler (1996), Evans and
Kaminski (1998), Green et al. (2004), and Kaminski and
Gradstein (2005). For the sake of brevity, the synonymy lists
only primary references, revisions of primary types, and/or
modified or tentative identifications.
? Ammobaculites jarvisi Cushman and Renz 1946
Plate 4, figure 2
Ammodiscus spp.
Deformed or poorly preserved specimens with no affinities to
known species of Ammodiscus.
Ammolagena clavata (Jones and Parker 1860)
Plate 2, figures 3a,b, 4
Trochammina irregularis (d’Orbigny) var. clavata JONES and
PARKER 1860, p. 304.
Ammolagena clavata (Jones and Parker 1860).– KAMINSKI and
GRADSTEIN 2005, p. 165, pl. 21, figs. 1-6 (figure 1 is the lectotype).
? Ammobaculites jarvisi CUSHMAN and RENZ 1946, p. 19, pl. 2, figs.
8,9.
Ammolagena sp.
Ammodiscus incertus d’Orbigny 1839
Ammodiscus incertus D’ORBIGNY 1839, p. 49.
Broken specimen of Ammolagena clavata without a visible
proloculus.
Ammodiscus peruvianus Berry 1928
Ammosphaeroidina sp.
Plate 1, figure 20
Plate 2, figure 5
Plate 4, figure 5a,b,c
Ammodiscus peruvianus BERRY 1928, p. 342, pl. 27.
?Cystaminella pseudopauciloculata MJATLIUK 1966, p. 264, pl. 1,
figs. 5-7; pl. 2, fig. 6; pl. 3, fig. 3.
Ammodiscus tenuissimus Grzybowski 1898
Plate 1, figure 21
Ammodiscus tenuissimus GRZYBOWSKI 1898, p. 282, pl. 10, fig. 35.
Specimens are closest to Ammosphaeroidina pseudopauciloculata (Mjatliuk).
PLATE 1
1-2 Rhabdammina abyssorum [64R-3, 40-41.5cm]
860µm, 924µm
3 Rhabdammina sp. [69R-5, 38.5-40cm] 743µm
4 Bathysiphon sp. 1 [68R-3, 40-41.5cm] 600µm
5-7 Nothia spp. [61R-3, 36-38cm] 500µm, [81R-1,
40.5-42cm] 1321µm, [72R-3, 37.5-39cm] 822µm
8 Nothia excelsa [69R-5, 38.5-40cm] 559µm
382
13 Lagenammina sp. [71R-3, 38-39.5cm] 518µm
14 Lagenammina sp. [80R-1, 40-41.5cm] 517µm
15 Psammosphaera fusca [70R-1, 38.5-40cm] 920µm
16 Hyperammina elongata [69R-1, 38.5-40cm] 866µm,
17 Hyperammina rugosa [91R-2, 38-40cm] 376µm
18-19 Hyperammina elongata [73R-3, 38.5-40cm] 906µm,
[91R-2, 38-40cm] 1162µm
9-10 Nothia spp. [85R-1, 40-41.5cm] 1390µm, [76R-3,
40-41.5cm] 770µm
20 Ammodiscus peruvianus [64R-3, 40-41.5cm] 223µm
11-12 Rhizammina spp. [87R-2, 40-42cm] 2151µm, [92R-1,
38.5-40.5cm] 244µm
21 Ammodiscus tenuissimus [64R-3, 40-41.5cm] 255µm.
(If not labeled, scale bar = 400µm).
M. A. Kaminski et al.
micropaleontology, vol. 51, no. 5, 2005 (2006)
Plate 1
383
M. A. Kaminski et al.: Miocene foraminifera from ODP Hole 909c: Paleoceanography of the Fram Strait Area, Greenland Sea
Aschemocella grandis (Grzybowski 1898)
Conotrochammina sp.
Reophax grandis GRZYBOWSKI 1898, p. 277, pl. 10, figs 13-15.
Aschemocella subnodosiformis (Grzybowski 1898).– KAMINSKI and
GEROCH 1993, p. 249, pl. 2, figs. 8-10.
Plate 5, figure 3a,b,c
Aschemocella sp.
Cribrostomoides spp.
Deformed and broken chambers resembling Aschemocella
subnodosiformis (Grzybowski 1898).
Aschemocella subnodosiformis (Grzybowski 1898)
Hyperammina subnodosiformis GRZYBOWSKI 1898, p. 274, pl. 10,
figs 5-6.
Aschemocella subnodosiformis (Grzybowski 1898).– KAMINSKI and
GEROCH 1993, p. 249, pl. 1, figs. 10a-13.
Fine grained specimens, belonging to genus Conotrochammina.
Includes mostly deformed specimens that are probably closest
to C. subglobosus (Cushman 1910).
Cyclammina placenta (Reuss 1851)
Nonionina placenta REUSS 1851, p. 72, fig. 33a,b.
Cyclammina placenta (Reuss).– GRADSTEIN et al. 1994, pl. 6, figs
7-11.
Includes specimens with slightly sigmoidal final sutures that are
transitional to C. cancellata.
Bathysiphon sp. 1
Plate 1, figure 4
Fragments of elongate cylindrical tubes, thin walled and finely
agglutinated.
Cyclammina cancellata Brady 1879
Cyclammina cancellata BRADY 1879, p. 62.– BRADY 1884, pl. 37,
figs 8-15.
Bathysiphon sp. 2
The largest Cyclammina in our material, with sigmoidal sutures
and up to 16 chambers in the final whorl.
Similar to Bathysiphon sp. 1, but about three times wider.
Bathysiphon sp. 3
Cyclammina sp.
Similar to Bathysiphon sp. 1, but about twice the width.
Plate 7, figure 3a,b,c
Budashevaella multicamerata (Voloshinova and Budasheva 1961)
Smaller than C. cancellata, with a subacute periphery and only
a few supplementary apertures.
Plate 4, figure 6a,b
Circus multicameratus VOLOSHINOVA and BUDASHEVA 1961, p.
201, pl. 7 figs. 6a-c, pl. 7, figs. 4-5.
Budashevaella sp. 1
Eratidus sp.
Plate 4, figures 3, 4
Specimen are closest to Budashevaella multicamerata
(Voloshinova and Budasheva 1961).
Specimens are smaller and have a narrower uniserial portion
compared with the modern species E. foliaceus (Brady).
Budashevaella sp. 2
Glomospira spp.
Includes smaller specimens with about 7-8 chambers in the last
whorl, oval in outline, which resemble the Paleocene species B.
trinitatensis.
Specimens most closely resemble Glomospira gordialis (Jones
and Parker).
Haplophragmoides cf. H. bradyi (Robertson 1891)
cf. Trochammina bradyi ROBERTSON 1891, p. 388.
PLATE 2
1 Ammodiscus sp. 2 [78R-1, 40-42cm] 1536µm
2 Ammodiscus sp. 1 [87R-1, 40-42cm] 362µm
3 Ammolagena sp. attatched to Reticulophragmium sp.
[70R-3, 37.5-39.5cm] 596µm
4 Ammolagena clavata attatched to Cyclammina sp.
[75R-5, 40-41.5cm] 1800µm
5 Ammolagena sp. attatched to Nothia sp. [81R-1,
40.5-42cm] 1321µm
6 Rhizammina sp. (Tolypammina vagans of Spiegler)
[72R-1, 37.5-39cm] 612µm
7-8 Repmanina charoides [68R-4, 38.5-40cm] 341µm,
[62R-5, 38-40cm] 327µm
384
9-11 Psamminopelta gradsteini [94R-1, 40-41.5cm]
382µm, [95R-1, 42-43.5cm] 174µm, [61R-5, 37.539cm] 455µm
12 Psamminopelta sp. [95R-1, 42-43.5cm] 267µm
13 Spirosigmoilinella compressa [60R-1, 38.5-40cm]
504µm
14-15 Hormosinella carpenteri [67R-3, 40-41.5cm]
1467µm, [94R-3, 35-36.5cm] 1826µm
16-18 Reophanus berggreni [94R-3, 35-36.5cm] 2259µm,
[93R-1, 40-41.5cm] 2000µm, [94R-1, 40-41.5cm]
2032µm. (If not labeled scale bar = 400µm).
M. A. Kaminski et al.
micropaleontology, vol. 51, no. 5, 2005 (2006)
Plate 2
385
M. A. Kaminski et al.: Miocene foraminifera from ODP Hole 909c: Paleoceanography of the Fram Strait Area, Greenland Sea
Haplophragmoides cf. H. bradyi (Robertson 1891).– GREEN et al.
2004, p. 124, pl. 1, figs. 5-7.
Slightly larger than the typical modern form. It most closely resembles the specimens from the Gulf of Mexico illustrated by
Green et al. (2004).
Haplophragmoides ex gr. H. carinatus Cushman and Renz 1941
Plate 3, figures 12a,b,c, 14a,b, 15a,b
Haplophragmoides carinatus CUSHMAN and RENZ 1941, p. 2, pl. 1,
fig. 1.– SCHRÖDER-ADAMS and MCNEIL 1994, p. 38, pl. 4, figs.
9-13.
The morphology of the species is quite variable, and some transitional forms may be present. We use the term in a broad sense,
following Schröder-Adams and McNeil (1994).
Haplophragmoides sp. 4
These are mostly flattened specimens with a thin wall and 4-5
chambers, which most closely resemble H. bradyi (Robertson
1891).
Haplophragmoides sp. 5
Flat specimens with more than 5 chambers, which most closely
resemble Haplophragmoides stomatus (Grzybowski).
Haplophragmoides sp. 6
A large, flat, thin-walled form with a round open umbilicus and
6 to 6 1/2 chambers.
Haplophragmoides spp.
Plate 4, figure 1a,b
Includes the broken, deformed specimens whose affinity to genus Haplophragmoides is only tentative.
Haplophragmoides walteri/carinatus transitional form
Plate 3, figure 11
Haplophragmoides walteri (Grzybowski 1898)
Transitional forms between H. carinatus and H. walteri.
Plate 3, figure 10a,b
Haplophragmoides eggeri Cushman 1926
Haplophragmoides eggeri CUSHMAN 1926, p. 583, pl. 15, figs. 1a,b.
Haplophragmoides aff. H. horridus (Grzybowski 1901)
Trochammina walteri GRZYBOWSKI 1898, p. 290, pl. 11, fig. 31.
Haplophragmoides walteri (Grzybowski).– KAMINSKI and GEROCH
1993, p. 263, pl. 10, fig. 3a-7c.
aff. Haplophragmium horridum GRZYBOWSKI 1901, p. 270, pl. 7, fig.
12.
Hormosinella carpenteri (Brady 1881)
Our specimens have the distinctive triangular last chamber of
H. horridus, but differ in having only 5 chambers in the last
whorl.
Trochammina (Hormosina) carpenteri BRADY 1881, p. 51.
Hormosina carpenteri BRADY 1884, p. 327, pl. 39, figs. 14-18.
Haplophragmoides sp. 1
Plate 2, figures 14, 15
Specimens have large, irregular chambers.
Hormosinella sp.
Plate 3, figure 16a,b
The specimens are closest to Hormosinella carpenteri.
Flattened specimens that have fewer chambers than H.
carinatus.
Haplophragmoides sp. 2
Hyperammina elongata Brady 1878
Plate 1, figures 16, 18, 19a,b
Plate 3, figure 13
Hyperammina elongata Brady 1878.– OSTERMAN and SPIEGLER
1996, pl. 1, fig. 6.
Specimens that most closely resemble H. walteri, but have a
partial carina. Possibly transitional to H. carinatus.
Hyperammina rugosa Verdenius and Van Hinte 1983
Haplophragmoides sp. 3
Hyperammina rugosa VERDENIUS and VAN HINTE 1983, p. 187, fig.
16; pl. 1, figs. 12-14.
Deformed specimens that are closest to R. pusillum.
Plate 1, figure 17
PLATE 3
1 Subreophax sp. 1 [85R-2, 40-42cm] 368µm
2 Subreophax sp. 2 [74R-3, 40-41.5cm] 951µm
3-4 Pseudonodosinella nodulosa [61R-3, 36-38cm]
742µm, [64R-5, 38.5-40cm] 700µm
5 Reophax pilulifer [69R-3, 40-41.5cm] 1195µm
6 Reophax excentricus [55R-3, 40-41.5cm] 252µm
7-9 Reophax spp. [84R-1, 40-42cm] 580µm, [76R-3,
40-41.5cm] 721µm, [62R-5, 38-40] 959µm
10 Haplophragmoides walteri [64R-5, 38.5-40] 734µm
386
11 Haplophragmoides walteri / carinatus [55R-1, 41.543cm] 243µm
12 Haplophragmoides ex gr. carinatus [60R-5, 3940.5cm] 540µm
13 Haplophragmoides sp. 2 [91R-2, 38-40cm] 508µm
14-15 Haplophragmoides ex gr. carinatus [76R-5,
40-41.5cm] 635µm, [76R-5, 40-41.5cm] 831µm
16 Haplophragmoides sp. 1 [65R-3, 38.5-40cm] 320µm.
(If not labeled scale bar = 400µm).
M. A. Kaminski et al.
micropaleontology, vol. 51, no. 5, 2005 (2006)
Plate 3
387
M. A. Kaminski et al.: Miocene foraminifera from ODP Hole 909c: Paleoceanography of the Fram Strait Area, Greenland Sea
Hyperammina spp.
Unidentifiable fragments of different Nothia species.
Various unidentifiable deformed specimens belonging to the
genus Hyperammina.
Psamminopelta gradsteini Kaminski and Geroch 1997
Karreriella seigliei (Gradstein and Kaminski 1989)
Plate 7, figures 4, 5a,b, 6
Dorothia seigliei GRADSTEIN and KAMINSKI 1989, p. 79, textfig. 3,
pl. 5, figs. 1-6, pl. 6, figs. 1-5.
Karreriella seigliei (Gradstein and Kaminski 1989),– CHARNOCK and
JONES 1990, p. 194, pl. 12, fig. 16, pl. 25, fig. 7.
Plate 2, figures 9, 10, 11
Spirosigmoilinella compressa (Matsunaga 1955).– OSTERMAN and
SPIEGLER 1996, pl. 1, fig. 17.
Psamminopelta gradsteini KAMINSKI and GEROCH 1997, p. 250,
textfig. 1, pl. 1, figs. 1-9.
The species appears to be endemic to the Norwegian-Greenland
Sea region.
This thin, narrow species has been previously reported under
various names in the North Sea – Norwegian Sea literature. It is
also found in the North Atlantic and in the Polish Carpathians
(Kaminski and Geroch 1997).
Karreriella sp.
Psamminopelta sp.
Broken or deformed specimens closest to Karreriella seigliei.
Plate 2, figure 12
Karrerulina horrida (Mjatliuk 1970)
Specimens are similar to Psamminopelta gradsteini, but are
broader and less flattened.
Karreriella horrida MJATLIUK 1970, p. 114, pl. 4, fig. 9, pl. 33, figs
15, 16a-b.
Karrerulina horrida (Mjatliuk 1970).– KAMINSKI and GRADSTEIN
2005, p. 473, pl. 117, figs 1-11.
Karrerulina sp.
Broken or deformed specimens resembling Karrerulina
horrida (Mjatliuk 1970).
Psammosiphonella cylindrica (Glaessner 1937)
Rhabdammina cylindrica GLAESSNER 1937, p. 354, pl. 1, fig. 1.
Psammosiphonella cylindrica (Glaessner).– KAMINSKI and GRADSTEIN 2005, p. 119, pl. 5/6, figs 9-13.
Psammosiphonella discreta (Brady 1881)
Plate 1, figures 13, 14
Rhabdammina discreta BRADY 1881, p. 48.– BRADY 1884, p. 268, pl.
22, figs. 11-13.
Psammosiphonella discreta (Brady).– KAMINSKI and GRADSTEIN
2005, p. 117, pl. 4/5, figs 1-8.
Specimens are coarsely agglutinated.
Psammosphaera fusca Schultze 1875
Lagenammina sp.
Plate 1, figure 15
Nothia excelsa (Grzybowski 1898)
Plate 1, figure 8
Psammosphaera fusca SCHULTZE 1875, p. 113, pl. 2, fig. 8a-f.
Dendrophrya excelsa GRZYBOWSKI 1898, p. 272, pl. 10, figs. 1-4.
Nothia excelsa (Grzybowski).– GEROCH and KAMINSKI 1992, p.
255, pl. 1, figs. 1a-4, pl. 2, figs. 1-11.
Psammosphaera spp.
Nothia latissima (Grzybowski 1898)
Plate 3, figures 3, 4
Dendrophrya latissima GRZYBOWSKI 1898, p. 273, pl. 10, fig. 8.
Nothia latissima (Grzybowski).– KAMINSKI and GEROCH 1993, p.
245, pl. 1, figs. 1a-c, 14a,b.
Different species of Psammosphaera that are not identifiable.
Pseudonodosinella elongata (Grzybowski 1898)
Reophax elongata GRZYBOWSKI 1898, p. 279, pl. 10, figs. 19-20.
Pseudonodosinella elongata (Grzybowski).– KAMINSKI and GRADSTEIN 2005, p. 256.
Nothia robusta (Grzybowski 1898)
Dendrophrya robusta GRZYBOWSKI 1898, p. 273, pl. 10, fig. 7.
Nothia robusta (Grzybowski).– KAMINSKI and GRADSTEIN 2005,
p. 114, pl. 4, figs. 1-8 (fig. 1 is the lectotype).
Only fragments of this species were observed.
Pseudonodosinella nodulosa (Brady 1879)
Reophax nodulosa BRADY 1879, p. 52, pl. 4, figs 7-8.
Pseudonodosinella nodulosa (Brady).– KAMINSKI and GRADSTEIN
2005, p. 259, pl. 49, figs 1-9.
Nothia spp.
Plate 1, figures 5, 6, 7, 9, 10
PLATE 4
1 Haplophragmoides sp. [78R-1, 40-42cm] 471µm
7 Recurvoides sp. [63R-1, 42-43.5cm] 604µm
2 ?Ammobaculites jarvisi [94R-1, 40-41.5cm] 3369µm
8 Trochammina sp. 909 [74R-5, 40-42cm] 639µm
3-4 Eratidus sp. [81R-4, 39-45cm] 431µm, [62R-5,
38-40cm] 265µm
9 Trochammina lomonosovensis [60R-5, 39-40.5cm]
400µm
5 Ammosphaeroidina sp. [69R-5, 38.5-40cm] 439µm
10 Trochammina sp. [81R-4, 39-40.5cm] 546µm. (If not
labeled scale bar = 400µm).
6 Budashevaella multicamerata [55R-1, 41.5-43cm]
650µm
388
M. A. Kaminski et al.
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Plate 4
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M. A. Kaminski et al.: Miocene foraminifera from ODP Hole 909c: Paleoceanography of the Fram Strait Area, Greenland Sea
Recurvoides sp.
Reticulophragmium acutidorsatum (Hantken 1868)
Plate 4, figure 7a,b.
Plate 6, figure 3
Small streptospiral tests, relatively coarse grained, chambers increase rapidly in size.
Haplophragmium acutidorsatum HANTKEN 1868, p. 82, pl. 1, fig.
1a,b.
Reticulophragmium acutidorsatum (Hantken).– GELLAI-NAGY 1988,
pl. 1, figs. 1-3 (lectotype).
Recurvoidella lamella (Grzybowski 1898)
Trochammina lamella GRZYBOWSKI 1898, p. 290, pl. 11, fig. 25.
Recurvoidella lamella (Grzybowski 1898).– KAMINSKI and
GEROCH 1993, p. 263, pl. 10, figs. 8a-9c (figure 8 is the lectotype).
Reticulophragmium amplectens (Grzybowski 1898)
Recurvoidella sp.
Cyclammina amplectens GRZYBOWSKI 1898, p. 292, pl. 12, figs. 1-3
Reticulophragmium amplectens (Grzybowski).– KAMINSKI and
GEROCH 1993, p. 266, pl. 11, figs 5-7c
Resembling broken or deformed specimens similar to
Recurvoidella lamella (Grzybowski, 1898).
Plate 6, figure 4a,b
Reticulophragmium orbicularis (Brady 1881)
Plate 7, figure 2a,b,c
Reophanus berggreni Gradstein and Kaminski 1997
Cyclammina orbicularis BRADY 1881, p. 53.– BRADY 1884, pl. 37,
figs. 17-19.
Plate 2, figures 16, 17, 18
Hormosina carpenteri (Brady).– OSTERMAN and SPIEGLER 1996,
pl. 1, fig. 11.
Reophanus berggreni GRADSTEIN and KAMINSKI 1997, p. 220,
textfig. 4; fig. 5, 1-7b.
The specimens have the tangential sutures that are typical of the
modern form. This species probably forms a plexus with R.
rotundidorsata.
Reophax duplex Grzybowski 1896
Reticulophragmium pusillum (Brady 1881)
Reophax duplex var. alpha GRZYBOWSKI 1896, p. 276, pl. 8, figs.
23-24.
Plate 6, figures 1a,b, 2a,b
Reophax excentricus Cushman 1910
Cyclammina pusilla BRADY 1881, p. 53.
Plate 3, figure 6
Reticulophragmium rotundidorsatum (Hantken 1875)
Reophax excentricus CUSHMAN 1910, p. 92, textfig. 134.
Reophax sp. – OSTERMAN and SPIEGLER 1996, pl. 1, fig. 7.
Plate 6, figure 7a,b, Plate 7, figure 1a,b
Haplophragmium rotindidorsatum HANTKEN 1875, p. 12, pl. 1, fig. 2.
Reticulophragmium rotundidorsatum (Hantken).– HORVÁTH 2002, p.
31, pl. 2, fig. 2.
Reophax pilulifer Brady 1884
Plate 3, figure 5
Reticulophragmium sp. 1
Reophax pilulifer BRADY 1884, p. 292, pl. 30, figs 18-20.
Plate 6, figure 6a,b
Chambers increase in size more slowly compared with the modern species, as a result the specimens bear a resemblance to the
Paleogene species Hormosina trinitatensis.
Deformed specimens closest to Reticulophragmium rotundidorsatum, but differing in possessing a narrower test and thin wall.
Reophax spp.
Reticulophragmium sp. 2
Plate 3, figures 7-9
Different broken and deformed parts of species belonging to the
genus Reophax.
Deformed and broken specimens closest to Reticulophragmium
amplectens.
Reticulophragmium sp. 3
Deformed and broken specimens closest to Reticulophragmium
acutidorsatum.
Repmanina charoides (Jones and Parker 1860)
Plate 2, figures 7-8
Trochammina squamata var. charoides JONES and PARKER 1860, p.
304
Glomospira charoides (Jones and Parker).– BERGGREN and
KAMINSKI 1990, p. 60, pl. 1, fig. 2 (lectotype).
Reticulophragmium spp.
Plate 6, figure 5a,b
Specimens belonging to this genus that remain unidentified.
PLATE 5
1-2 Trochammina spp. [85R-1, 40-41.5cm] 737µm,
[81R-4, 39-40.5cm] 459µm
3 Conotrochammina sp. [91R-1, 38.5-40.5cm] 554µm
4 ?Karrerulina sp. fragment [73R-3, 38.5-40cm] 324µ
390
5 Veleroninoides sp. [73R-1, 38.5-40cm] 921µm
6–7 Veleroninoides scitulus [60R-5, 39-40.5cm] 630µm,
[68R-1, 40-41.5cm] 956µm. (If not labeled scale bar =
400µm).
M. A. Kaminski et al.
micropaleontology, vol. 51, no. 5, 2005 (2006)
Plate 5
391
M. A. Kaminski et al.: Miocene foraminifera from ODP Hole 909c: Paleoceanography of the Fram Strait Area, Greenland Sea
Rhabdammina abyssorum Carpenter 1869
Veleroninoides scitulus (Brady 1881)
Plate 1, figures 1,2
Plate 5, figures 6a,b, 7a,b
Rhabdammina abyssorum CARPENTER 1869, p. 288.– BRADY 1884,
p. 266, pl. 21, figs 1-13.
Lituola (Haplophragmium) scitulum BRADY 1881, p. 50. – BRADY
1884, pl. 34, figs. 11a-13.
Rhabdammina spp.
Veleroninoides sp.
Plate 1, figure 3
Plate 5, figures 5a,b,c
Broken parts of different unidentifiable species of genus
Rhabdammina.
Specimens resembling Veleroninoides scitulus in chamber arrangement, but differing in possessing a shallower umbilicus
and a more finely finished wall.
Rhizammina spp.
Plate 1, figures 11, 12; Plate 2, figure 6
REFERENCES
Different broken and deformed fragments of Rhizammina sp. 1
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ALTENBACH, A., PFLAUMANN, U., SCHIEBEL, R., THIES, A.,
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carbon. Journal of Foraminiferal Research, 29 (3): 173-185.
Saccammina cf. S. sphaerica Brady 1879
cf. Saccammina sphaerica SARS. – BRADY 1879, p. 183
Specimens differ from the modern form in their smaller dimensions and more finely agglutinated wall.
Spirosigmoilinella compressa Matsunaga 1955
Plate 2, figure 13
Spirosigmoilinella compressa MATSUNAGA 1955, p. 50, figs. 1-2.
Spirosigmoilinella sp. – OSTERMAN and SPIEGLER 1996, pl. 1, fig.s
15-16.
Spirosigmoilinella sp.
Specimens resembling Spirosigmoilinella compressa Matsunaga 1955.
Subreophax sp. 1
Plate 3, figure 1
Specimens are most similar to the modern species Subreophax
aduncus (Brady).
Subreophax sp. 2
Plate 3, figure 2
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Specimens with more elongated, irregular chambers.
Trochammina lomonosovensis Evans and Kaminski 1998
Plate 4, figure 9a,b
Trochammina lomonosovensis EVANS and KAMINSKI 1998, p. 124,
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Plate 4, figures 8, 10a,b; Plate 5, figures 1a,b,c, 2a,b
Different undetermined types of genus Trochammina.
PLATE 6
1-2 Reticulophragmium pusillum [86R-1, 41-42.5cm]
1107µm, [87R-1, 40-42cm] 391µm
3 Reticulophragmium acutidorsatum [65R-1, 38.540cm] 594µm
4 Reticulophragmium amplectens [65R-5, 38.5-40cm]
464µm,
392
5 Reticulophragmium sp. [55R-1, 41.5-43cm] 640µm
6 Reticulophragmium sp. 1 [91R-2, 38-40cm] 779µm
7 Reticulophragmium rotundidorsatum [93R-1, 4041.5cm] 529µm. (If not labeled, scale bar = 400µm).
M. A. Kaminski et al.
micropaleontology, vol. 51, no. 5, 2005 (2006)
Plate 6
393
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PLATE 7
1 Reticulophragmium rotundidorsatum [65R-1, 38.540cm] 414µm
2 Reticulophragmium orbicularis [66R-1, 38.5-40cm]
947µm
394
3 Cyclammina sp. [82R-1, 40-41.5cm] 1668µm
4–6 Karreriella siegliei 4, [94R-3, 35-36.5cm] 484µm; 5,
[64R-1, 37.5-39cm] 460µm; 6, [60R-3, 37.5-39cm]
928µm. (If not labeled, scale bar = 400µm).
M. A. Kaminski et al.
micropaleontology, vol. 51, no. 5, 2005 (2006)
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